Aspects of Palaeoproterozoic orogenesis in the Gawler Craton: the c Ma Cornian Orogeny

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1 New geology Aspects of Palaeoproterozoic orogenesis in the Gawler Craton: the c Ma Cornian Orogeny Anthony J Reid 1 and Martin P Hand 2 1 Geological Survey Branch, PIRSA 2 School of Earth and Environmental Sciences, University of Adelaide 1 For example, Alpine-Himalayan geologists need only debate about the mechanisms of tectonism; they at least know where the palaeosubduction zone was. In the Gawler Craton, we cannot even agree if there was a subduction zone, or two, let alone determine its polarity. Introduction Deciphering the geological evolution of Precambrian terranes is an inherently difficult task since the boundary conditions that influenced the tectonic events recorded in the rock record are typically absent 1. Consequently, the palaeoconfigurations of Precambrian cratons and terranes are subject to much discussion, leading to the many debates as to the nature of various supercontinents in Earth history (e.g. Rhodinia, Columbia) or as to the Proterozoic evolution of Australia (Myers, Shaw and Tyler 1996; Betts and Giles 2006; Neumann and Fraser 2007). Nevertheless, tools such as zircon geochronology are able to resolve aspects of the regional geological evolution in typically polydeformed and often gneissic Precambrian terranes (e.g. Moller et al. 2007). In South Australia the major Precambrian terrane, the Gawler Craton, suffers not only from a lack of outcrop, but also from a comparatively small number of focused geochronological and geological studies able to define the regional tectonometamorphic evolution. Consequently, the framework within which mineral systems such as Olympic Dam or Challenger deposits developed has remained enigmatic. As highlighted by Hand, Reid and Jagodzinski (2007), significant ambiguities remain in terms of the timing and spatial distribution of the tectonic events within the craton, the tectonic settings of the major magmatic systems and the crust mantle evolution of the craton through time. Since the development of effective mineral exploration strategies is increasingly reliant on integrated, datarich tectonic models, it is likely that the lack of systematic tectonic analysis has been a factor in companies deciding not to undertake exploration in greenfield regions and is potentially hindering current exploration programs. Recent publication of historical zircon geochronology (Fanning, Reid and Teale 2007) and an emerging body of work from university researchers (Teasdale 1997; Betts, Valenta and Finlay 2003; Tomkins, Dunlap and Mavrogenes 2004; Swain et al. 2005; Payne, Barovich and Hand 2006) has built on the foundation work of the Geological Survey of South Australia (Drexel, Preiss and Parker 1993; Daly, Fanning and Fairclough 1998; Ferris, Schwarz and Heithersay 2002) and is shedding further light on these large-scale geological issues. In this article we present an overview of our recent work (Reid et al. 2008) on a major magmatic system on the eastern Gawler Craton, the c Ma Donington Suite, and give evidence for a revision of nomenclature and models for Palaeoproterozoic orogenesis in the Gawler Craton. In the eastern Gawler Craton the Donington Suite forms part of the basement to both Palaeoproterozoic bimodal volcano-sedimentary successions and Mesoproterozoic magmatism, both of which contain a variety of mineralisation types and significant mineralisation potential (Daly, Fanning and Fairclough 1998). Understanding the evolution of the basement to these sequences may provide clues as to the tectonic framework within which these younger thermal and sedimentary events occurred. Geological setting The Donington Suite (Schwarz 2003) is a linear batholith some 60 km wide and up to 600 km in N S extent, forming a significant component of the eastern Gawler Craton (Fig. 1). While not itself metallogenically fertile, the Donington Suite is imaged on regional seismic cross-sections as forming the basement to Olympic Dam (Drummond et al. 2006) and hosts the mineralisation at the Carrapateena prospect (Jagodzinski et al. 2007). Predominant outcrop of the Donington Suite occurs in the southern Gawler Craton as spectacular coastal exposures on the Eyre and Yorke peninsulas. The Donington Suite is dominated by granodiorite gneiss, but also includes a wide range of lithologies such as pyroxene-bearing charnockite, megacrystic alkali-feldspar granite and gabbronorite along with co-magmatic mafic units (Mortimer, Cooper and Oliver 1988). Early workers considered the Donington Suite to belong to the Lincoln Complex, a rock association that was originally proposed to encompass magmatism that occurred synchronous with the Kimban Orogeny (Parker et al. 1993); however, recent revision of this nomenclature (Schwarz 2003) has seen the Donington Suite excluded from the Lincoln Complex as the timing and duration of the Kimban Orogeny has been clarified to the interval Ma (Ferris, Schwarz and Heithersay 2002). Zircon geochronology of the Donington Suite indicates that although its emplacement has been considered to be geologically instantaneous (e.g. Hoek and Schaefer 1998), SHRIMP data collected in more recent years shows ages span over a period of c. 14 million years with the suggestion of southward younging intrusive ages. Evidence of an older period of magmatic emplacement (c Ma) appears to be confined to the Olympic Domain (Jagodzinski et al. 2007). Geochemically, Donington Suite granitoids show LREE enrichment, negative Nb, Sr, P and Ti anomalies and 26 MESA Journal 50 September 2008

2 Cornian Orogeny km ' have εnd 1850 Ma values between 2 and 4 (Schaefer 1998). The Donington Suite is thought to be derived from a mixture of moderately juvenile mafic parent and pre-existing crustal material (Mortimer, Cooper and Oliver 1988; Schaefer 1998). The major Palaeoproterozoic orogenic phase recognised in the southeastern Gawler Craton is the Kimban Orogeny. The Kimban Orogeny was thought to have been long lived, occurring over the interval 1850 to 1700 Ma (Thompson 1969; Glen et al. 1977; Parker 1980; Daly, Fanning and Fairclough 1998; Zang and Fanning 2001). However, Hoek and Schaefer (1998) and Vassallo and Wilson (1999; 2002) have shown that a tectonic foliation developed within the Donington Suite prior to Ma reworking. From these observations, Hoek and Schaefer (1998) suggested the earlier foliation indicated the occurrence of a separate tectonothermal event or orogeny, and that the latter, Ma event alone should be considered as the Kimban Orogeny. This is ' Corny Point Undifferentiated Proterozoic Hiltaba Suite Gawler Range Volcanics Donington Suite Archaean- Palaeoproterozoic _013 Figure 1 Location of the Donington Suite within the eastern Gawler Craton, South Australia. (After Reid et al. 2008, fig. 2a; published with the permission of the Geological Society of Australia) Port Neil supported by the presence of several phases of sedimentation and volcanism between 1850 Ma and 1740 Ma, e.g. the Wallaroo Group and other units. This earlier, c Ma event has been variously termed the Lincoln Orogeny (Vassallo and Wilson 1999) or the Neill Event (Ferris, Schwarz and Heithersay 2002), however, little work has focused on evaluating the structural and metamorphic expression of 1850 Ma tectonism. The following observations and results derive from study of the exposures on southern Yorke Peninsula, in particular the outcrops at Corny Point. All data and observations given below are given in full in Reid et al. (2008), to which readers are referred. Structural constraints on 1850 Ma tectonism The gneissic foliation within the Donington Suite is variably deformed by foliation boudinage (Fig. 2a) and intrafolial, isoclinal folding (Fig. 2b) along with zones of pervasive ductile shear (Fig. 2c). These structures themselves are deformed by tight to open folds. Locally, weakly foliated megacrystic granite dykes appear to intrude along the axial plane of these late folds (Fig. 2d). A sample of one of these dykes yielded a SHRIMP U Pb zircon magmatic crystallisation age of 1846 ± 4 Ma (MSWD = 1.3; n = 25). Thus, the apparently contractional deformation recorded within the Donington Suite must have occurred prior to 1846 ± 4 Ma, that is, soon after the emplacement of the bulk of the suite at c Ma (Jagodzinski et al. 2007). A series of shear zones are observed to overprint all structural fabrics within the Donington Suite on southern Yorke Peninsula. These shear zones vary from discrete metre-scale, mylonitic shear zones (Fig. 3a) to zones of pervasive reworking of the earlier fabric with minimum widths in the order of tens of metres. Importantly, these shear zones consistently show south-sidedown, normal kinematics (Fig. 3b) and a shallow (15º) to moderately (60º) west-plunging stretching lineation. The geometry and stretching lineation orientation of these shear zones suggest they resulted from extension coupled with a component of dextral strikeslip deformation. At a number of localities microgranite dykes intrude and are deformed by these late stage shear zones (Fig. 3c). One of these dykes yielded a SHRIMP U Pb zircon magmatic crystallisation age of 1843 ± 5 Ma (MSWD = 1.5; n = 16). Thus, these broadly extensional shear zones are therefore interpreted to have formed soon after the early contractional deformation. Notably, straight-sided mafic dykes are commonly emplaced sub-parallel to the gneissic fabric of these shear zones, and may also indicate lithospheric extension occurred at this time. Metamorphic constraints on 1850 Ma tectonism Corny Point is one of the few localities on southern Yorke Peninsula where diagnostic metamorphic mineral assemblages occur. At Corny Point, garnet-bearing quartzofeldspathic gneiss shows complex networks of garnet-bearing leucosomes (Figs 4a, b). These leucosomes occur in rocks that contain a biotite-defined foliation along MESA Journal 50 September

3 New geology (a) (b) (c) (d) 1846 ± 4 Ma _014 Figure 2 Compression-related structures within the Donington Suite, Yorke Peninsula. (a) Discordantly migmatised granodiorite gneiss of the Gleesons Landing Granite, deformed by foliation boudinage at Royston Head. (b) Strongly deformed layered granite-gneiss, Point Yorke. Inset shows isoclinal folds. Width of view of inset is ~10 cm. (c) Sheared megacrystic granite-gneiss of the Gleesons Landing Granite, Berry Bay. Photo taken looking west. (d) Dyke of feldspar-rich megacrystic granite, Royston Head. U Pb zircon SHRIMP age of this syn-contractional dyke is shown. (After Reid et al. 2008, figs. 5a, b, d, e; published with the permission of the Geological Society of Australia) with matrix of plagioclase and quartz. This suggests the leucosomes may have formed via the general reaction: biotite + sillimanite + quartz + plagioclase = garnet + melt ± K-feldspar (Spear 1993). The peak assemblage does not contain sillimanite, suggesting this reaction was terminated by the exhaustion of sillimanite and probably formed at conditions of ~6 kbar and ~750 C. Zircons preserved within a garnet-bearing leucosome yielded a magmatic crystallisation age of 1848 ± 8 Ma along with a number of older c Ma ages, interpreted to be detrital zircons scavenged from the surrounding metasedimentary rocks. The peak garnet has been partially replaced by intergrowths of biotite + cordierite ± sillimanite (Fig. 4c). This retrograde assemblage is a typical response to high-temperature decompression (e.g. Harley and Carrington 2001; Pitra and de Waal 2001; White, Powell and Holland 2001). Chemical U Th Pb electron microprobe ages from monazites within retrograde biotite yield a minimum estimate for the timing of retrogression of ~1830 Ma (Fig. 4d) indicating decompression may be linked to the development of the broadly extensional shear zones and that the clockwise P T path occurred during a single tectonothermal cycle. Orogenesis in the southeastern Gawler Craton: the c Ma Cornian Orogeny The c Ma event is characterised by the emplacement of the Donington Suite into a compressional tectonic environment. Contractional deformation was terminated by high temperature, extensional to strike-slip deformation. Our U Pb zircon geochronology shows that syn-contractional, synmetamorphic and syn-extensional magmatism occurred within error of each other, and probably over an interval of, at most, 10 million years. Thus, in our interpretation c Ma contractional deformation and amphibolite to granulite facies peak metamorphism were transient and the entire tectonothermal cycle occurred within 10 million years. This description of the c Ma event shows it to be far from the simple low-strain environment envisioned previously (Mortimer, Cooper and Oliver 1988; Hoek and 28 MESA Journal 50 September 2008

4 Cornian Orogeny (a) shear zone However, these terms are unsatisfactory since they derive from localities on the Eyre Peninsula where the geological record is dominated by reworking associated with the Ma Kimban Orogeny. In particular, we note that the use of the term Neill Event is highly unsatisfactory since Port Neill is the type locality of the Kalinjala Mylonite Zone (Parker 1980), which itself is the type example of a structure developed during the Kimban Orogeny. Therefore, we suggest the term Cornian Orogeny for this event in recognition of the excellent record of 1850 Ma tectonism preserved on Yorke Peninsula and in particular the exposures at Corny Point. A possible tectonic setting Detrital zircons from the Corny Point Paragneiss (Zang and Fanning 2001; Howard et al. 2006; Reid et al. 2008) yield ages as young as c.1870 Ma, suggesting the sedimentary precursor was deposited less than 20 million years prior to emplacement of the Donington Suite. The tectonic setting for the Cornian Orogeny was a system that underwent rapid switches in tectonic mode, such that a sedimentary basin underwent transient contractional deformation and granite emplacement, before reverting to a state of extension within a time interval of ~10 million years. Changes in subduction zone dynamics play a decisive role in the deformational history of regions above and inboard of the subduction zone and rapid switches from extension to compression are well documented and may also affect regions inboard hundreds of kilometres from an active subduction zone, as has been inferred for the Lachlan Fold Belt (Collins 2002). Since there is no geochemical evidence to suggest the Donington Suite formed in a subduction zone setting (Mortimer, Cooper and Oliver 1988; Schaefer 1998; Reid et al. 2008), we suggest a tectonic scenario in which the Donington Suite formed in a (far-field?) back-arc setting as a result of extensional melting of thinned back-arc lithosphere. The deformation and metamorphism of the Cornian Orogeny may have been focused into this back-arc due to the thermal softening of the thinned lithosphere (e.g. Thompson et al. 2001), as a result of a change in subduction dynamics, such as the arrival of a buoyant collider at a far-field subduction zone. (b) (c) 2 cm 1843 ± 5 Ma Figure 3 Extension-related structures within the Donington Suite, Yorke Peninsula. (a) Example of narrow high-temperature shear zone, Royston Head. (b) Detail of kinematic indicator (s-type porphyroclast) within sheared granite gneiss, indicating a south-side-down motion, The Gap. (c) Example of dated microgranite that crosscuts the extensional shear fabric within the Donington Suite, The Gap. U Pb zircon SHRIMP age of this syn- to post-extensional microgranite is shown. (After Reid et al. 2008, figs. 5f, 8b (part); published with the permission of the Geological Society of Australia) Schaefer 1998). We firstly suggest that the name for this event be revised. Previously this event was included as an early part of the Kimban Orogeny (Drexel, Preiss and Parker 1993), or has been termed the Lincoln Orogeny (Vassallo and Wilson 1999) or Neill Event (Ferris, Schwarz and Heithersay 2002). Acknowledgements Liz Jagodzinski (PIRSA) undertook the U Pb geochronology presented in this study, and Dave Kelsey (University of Adelaide) assisted in definition of the metamorphic P T path. Their efforts in helping to unravel the Cornian Orogeny are greatly appreciated. Michael Schwarz (Monax Mining Limited) is acknowledged for support of this project in its early stages, and his assistance in the field. Reviewers of the Australian Journal of Earth Sciences paper are also thanked for their input. This study was funded by PIRSA via ARC (Australian Research Council) Linkage Grant LP MESA Journal 50 September

5 New geology (a) (b) 1848 ± 8 Ma (c) (d) bi cd gt gt bi _016 Figure 4 Metamorphic characteristics of metapelites at Corny Point, the Corny Point Paragneiss of Zang and Fanning (2001). (a) Garnet-biotitequartzo-feldspathic gneiss, with garnet bearing leucosomes and leucocratic layering. (b) Detail of garnet-bearing leucosome. (c) Cordierite + biotite pseudomorph of garnet. Minor sillimanite is also present in this example. Field of view 12 mm. (d) Biotite corona around garnet. Also observed are radiation damage halos caused by monazite within the biotite. Chemical U Th Pb dating of monazite from this sample gave an age of 1827 ± 18 Ma (n = 35; MSWD = 1). Field of view 8 mm. (After Reid et al. 2008, figs. 10c, e; published with the permission of the Geological Society of Australia) References Betts PG and Giles D The Ma tectonic evolution of Australia. Precambrian Research 144: Betts PG, Valenta RK and Finlay J Evolution of the Mount Woods Inlier, northern Gawler Craton, southern Australia; an integrated structural and aeromagnetic analysis. Tectonophysics 366: Collins WJ Nature of extensional accretionary orogens. Tectonophysics 21:1 6. Daly SJ, Fanning CM and Fairclough MC Tectonic evolution and exploration potential of the Gawler Craton, South Australia. AGSO Journal of Australian Geology & Geophysics 17: Drexel JF, Preiss WV and Parker AJ eds The Geology of South Australia: Volume 1, The Precambrian, Bulletin 54. Geological Survey of South Australia, Adelaide. Drummond B, Lyons, P, Goleby B and Jones L Constraining models of the tectonic setting of the giant Olympic Dam iron oxide copper gold deposit, South Australia, using deep seismic reflection data. Tectonophysics 420: Fanning CM, Reid A and Teale G A geochronological framework for the Gawler Craton, South Australia, Bulletin 55. Geological Survey of South Australia, Adelaide. Ferris GM, Schwarz MP and Heithersay P The geological framework, distribution and controls of Fe-oxide and related alteration, and Cu-Au mineralisation in the Gawler Craton, South Australia, Part I: geological and tectonic framework. In TM Porter ed., Hydrothermal iron oxide copper gold and related deposits: a global perspective, vol. 2. PGC Publishing, Adelaide, pp Glen RA, Liang WP, Parker AJ and Rutland RW Tectonic relationships between the Proterozoic Gawler and Willyama orogenic domains. Geological Society of Australia Journal, 24: Hand M, Reid A and Jagodzinski E Tectonic framework and evolution of the Gawler Craton, South Australia. Economic Geology 102: Harley SL and Carrington DP The distribution of H 2 O between cordierite and granitic melt; H 2 O incorporation in cordierite and its application to high-grade metamorphism and crustal anatexis. Journal of Petrology 42: Hoek JD and Schaefer BF Palaeoproterozoic Kimban mobile belt, Eyre Peninsula; timing and significance of felsic and mafic magmatism and deformation. Australian Journal of Earth Sciences 45: Howard KE, Reid AJ, Hand MP, Barovich KM and Belousova EA Does 30 MESA Journal 50 September 2008

6 Cornian Orogeny the Kalinjala Shear Zone represent a palaeo-suture zone? Implications for distribution of styles of Mesoproterozoic mineralisation in the Gawler Craton. MESA Journal, 43:6 11. Department of Primary Industries and Resources South Australia, Adelaide. Jagodzinski EA, Reid AJ, Chalmers NC, Swain S, Frew RA and Foudoulis C Compilation of SHRIMP U-Pb geochronological data for the Gawler Craton, South Australia, 2007, Report Book 2007/21. Department of Primary Industries and Resources South Australia, Adelaide. Moller C, Andersson J, Lundqvist I and Hellstrom F Linking deformation, migmatite formation and zircon U-Pb geochronology in polymetamorphic terranes. Journal of Metamorphic Geology 25: Mortimer GE, Cooper JA and Oliver RL The geochemical evolution of Proterozoic granitoids near Port Lincoln in the Gawler orogenic domain of South Australia. Precambrian Research 40 41: Myers JS, Shaw RD and Tyler IM Tectonic evolution of Proterozoic Australia. Tectonics 15: Neumann NL and Fraser GL eds Geochronological synthesis and timespace plots for Proterozoic Australia, Record 2007/06. Geoscience Australia, Canberra. Parker AJ Stratigraphic subdivision of the Hutchison Group on northeastern Eyre Peninsula. In AJ Parker ed., Symposium on the Gawler Craton. Journal of the Geological Society of Australia 27:1 2. Parker AJ, Daly SJ, Flint DJ, Flint RB, Preiss WV and Teale GS Palaeoproterozoic. In JF Drexel, WV Preiss and AJ Parker eds, The geology of South Australia, Volume 1, The Precambrian, Bulletin 54. Geological Survey of South Australia, Adelaide, pp Payne J, Barovich K and Hand M Provenance of metasedimentary rocks in the northern Gawler Craton, Australia: implications for Palaeoproterozoic reconstructions. Precambrian Research 148: Pitra P and de Waal SA Hightemperature, low-pressure metamorphism and development of prograde symplectites, Marble Hall Fragment, Bushveld Complex (South Africa). Journal of Metamorphic Geology 19: Reid A, Hand M, Jagodzinski E, Kelsey D and Pearson NJ Palaeoproterozoic orogenesis within the southeastern Gawler Craton, South Australia. Australian Journal of Earth Sciences 55: Schaefer BF Insights into Proterozoic tectonics from the southern Eyre Peninsula, South Australia. PhD thesis, University of Adelaide. Schwarz MP LINCOLN, South Australia, 1: Geological Series Explanatory Notes, sheet SI Department of Primary Industries and Resources South Australia, Adelaide. Spear FS Metamorphic phase equilibria and pressure temperature time paths. Mineralogical Society of America Monograph 1. Swain G, Woodhouse A, Hand M, Barovich K, Schwarz M and Fanning CM Provenance and tectonic development of the late Archaean Gawler Craton, Australia; U-Pb zircon, geochemical and Sm-Nd isotopic implications. Precambrian Research 141: Teasdale J Methods for understanding poorly exposed terranes: the interpretive geology and tectonothermal evolution of the western Gawler Craton. PhD thesis, University of Adelaide. Thompson AB, Schulmann K, Jezek J and Tolar V Thermally softened continental extensional zones (arcs and rifts) as precursors to thickened orogenic belts. Tectonophysics 332: Thompson BP Precambrian crystalline basement. In LW Parkin ed., Handbook of South Australian geology. Geological Survey of South Australia, Adelaide, pp Tomkins AG, Dunlap WJ and Mavrogenes JA Geochronological constraints on the polymetamorphic evolution of the granulite-hosed Challenger gold deposit: implications for assembly of the northwest Gawler Craton. Australian Journal of Earth Sciences 51:1 14. Vassallo JJ and Wilson CJL Palaeoproterozoic geology of southeastern Eyre Peninsula, South Australia. In CJL Wilson ed., The Great Southern Transect II: a geological section incorporating the Lachlan Fold Belt, Adelaide Fold Belt and Gawler Craton, Halls Gap (Victoria) to Port Lincoln (SA), Field Guide 6: Geological Society of Australia, Specialist Group in Tectonics and Structural Geology. White RW, Powell R and Holland TJB Calculation of partial melting equilibria in the system Na 2 O-CaO-K 2 O-FeO- MgO-Al 2 O 3 -SiO 2 -H 2 O (NCKFMASH). Journal of Metamorphic Geology 19: Zang W and Fanning CM Age of the Kimban Orogeny revealed: U-Pb dates on the Corny Point Paragneiss, Yorke Peninsula. MESA Journal 23: Department of Primary Industries and Resources South Australia, Adelaide. For further information contact Anthony Reid, phone , <reid. anthony@saugov.sa.gov.au>. MESA Journal 50 September

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